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Article

Geochemical and Mineralogical Characteristics of the Middle Jurassic Coals from the Tongjialiang Mine in the Northern Datong Coalfield, Shanxi Province, China

by
Yue Yuan
1,2,3,
Shuheng Tang
1,2,3,* and
Songhang Zhang
1,2,3
1
School of Energy Resources, China University of Geosciences (Beijing), Beijing 100083, China
2
Beijing Key Laboratory of Unconventional Natural Gas Geological Evaluation and Development Engineering, China University of Geosciences, Beijing 100083, China
3
Coal Reservoir Laboratory of National Engineering Research Center of CBM Development & Utilization, China University of Geosciences, Beijing 100083, China
*
Author to whom correspondence should be addressed.
Minerals 2019, 9(3), 184; https://doi.org/10.3390/min9030184
Submission received: 24 January 2019 / Revised: 8 March 2019 / Accepted: 12 March 2019 / Published: 16 March 2019
(This article belongs to the Collection Critical Metals and Minerals in Coal and Coal Combustion Products)
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Abstract

:
There is limited information available on the minerals and elements present in the Jurassic coals from Datong Coalfield. This paper investigates the geochemical and mineralogical characteristics of the Middle Jurassic coals from the Tongjialiang Mine using X-ray powder diffraction (XRD), X-ray fluorescence spectrometry (XRF), inductively coupled plasma mass spectrometry (ICP-MS), and scanning electron microscopy in combination with energy-dispersive X-ray spectrometry (SEM-EDS). No.12 coal is a low-medium volatile bituminous coal and is characterized by low ash yield content, low moisture content, and ultra-low sulfur content. Compared with Chinese coals, the Tongjialiang coals have slightly higher average percentages of MgO and P2O5, and lower average percentages of the other major oxides, including SiO2, TiO2, Al2O3, Fe2O3, CaO, MnO, Na2O, and K2O. Compared with the World hard coals, Be, Cr, Co, Ni, Ge, Sn, Ta, and W are slightly enriched in the Tongjialiang coals. The concentrations of Li, F, Sc, V, Cu, Ga, Se, Sr, Zr, Nb, Hf, Pb, Th, and U are close to the average values of the world’s hard coals. The minerals in No.12 coal mainly include quartz, kaolinite, siderite, and ankerite, along with smaller amounts of pyrite, illite, calcite, and rutile. The formation of syngenetic siderite in No.12 coal is related to the weathering of biotite in the gneiss of the Yinshan Upland. The modes of occurrence of ankerite indicate that the coals may be affected by the injection of low temperature hydrothermal fluids. It is noteworthy that a portion of epigenetic ankerite may be a product of metasomatism between syngenetic siderite and the epigenetic Fe-Mg-Ca rich hydrothermal fluids. The ratios of Al2O3/TiO2, REY (rare earth elements and yittrium) enrichment patterns, the modes of occurrence of siderite and ankerite, as well as the enriched lithophile and siderophile elements indicate that the No.12 coal may have originated from the Yinshan Upland and may also have been influenced by low temperature hydrothermal fluids that might have circulated in the coal basin.

1. Introduction

In China, coal reserves are abundant, and coal is considered to be the most important mining resource. Under some specific geological conditions, coals may be enriched in some metal elements [1,2,3]. Understanding the concentrations, modes of occurrence, distributions, and origins of minerals and rare metal elements in coal would not only provide further evidence of the formation mechanisms for these rare metal elements, but also enhance the economic value of the coals that are enriched in rare metal components [4,5,6,7]. Moreover, the study of enrichment mechanisms of toxic elements in coals may be of great significance to reduce the adverse effects on human health and environment due to the release of toxic elements during the coal utilization [8,9,10]. Generally, minerals—as the main carrier of elements—are the most important inorganic components in coals. In some cases, elements such as Ge and U are bound in organic matters [11,12,13,14]. Additionally, it has been suggested that the minerals in coals might be used as indicators for the sediment source region, depositional conditions of the original peat swamp, geological history of coal-bearing sequences and the regional tectonics [15,16]. From the perspective of utilization, the minerals in coal would directly affect the calorific value of coal as well as the processing and utilization of coal. Improper combustion of coal and release of toxic elements present within it are also the main causes of pollution, corrosion and wear during coking [17]. The rational utilization of mineral resources plays an important role on the development of the economy and society [18,19].
The Datong Coalfield is one of the largest coal producers of China and is located in northern Shanxi Province, which is adjacent to Shaanxi Province, Hebei Province, and Inner Mongolia Autonomous Region (Figure 1). The Datong coal-bearing basin, consisting of the Late Paleozoic Permian-Carboniferous and the Mesozoic Jurassic coal-bearing strata, has attracted much attention for its special characteristics, such as basin evolution, sedimentation, coal formation, and metamorphism [20,21,22]. Some studies have shown that the late Paleozoic coals from Datong Coalfield are associated with high concentrations of some potentially valuable and toxic elements. For example, Li, F, Ga, Tl, Hg, and REY (rare earth elements and yitrrium) are slightly enriched in the No.4 coal from the Yongdingzhuang Mine [23]. Wang et al. reported that Ga and U are relatively enriched in the Permian-Carboniferous coals from the northern Datong Coalfield [24]. Another study reported that Mn, As, and Se have slightly higher concentration in the coals from Baidong Mine and Qifengshan Mine, which can have adverse effects on human health and environment during utilization [25]. Several potentially valuable elements, such as Al, Li, Ge, Zr, and Hf, and potentially toxic elements, including Be, As, Cd, and Pb, are slightly enriched in the No.5 coal from Yanzishan Mine (data not published yet).
In the Early and Middle Jurassic, the coal-bearing rock series which were deposited under the fluvial and lacustrine sedimentary environment were superimposed on the Late Paleozoic strata [20,21,22]. Thus, the extremely thick coal seams of the Datong Formation were formed, which are of significant industrial value today [20,21,22]. Previous investigations on geochemical and mineralogical characteristics of the Jurassic coals from the Datong Coalfield are very scarce.
The present paper investigates the mineralogical and geochemical characteristics of the Jurassic coals from the Datong Coalfield, in order to evaluate different geological factors that may have controlled the abundance and distribution of trace elements and minerals in the coals.

2. Geological Setting

The Datong Coalfield is located to the south of the Yinshan Upland and stretches 50 km long (NE–SW) and 30 km wide (NW–SE), covering a total area of 1900 km2 [20,21,22,26,27]. It is bound by the Pingwang-Emaokou fault to the west, by the Lvliang mountain syncline to the east, and by the Hongtao mountain syncline to the north [20,21,22,26,27]. The orogenic movement that occurred in the Early Paleozoic was defined by the Caledonian tectonic movement, which resulted in the uplift of the Datong coal-bearing basin [20,21,22,26,27]. The Datong basin with the Upper Carboniferous-Permian and Jurassic coal-bearing strata was formed after the Caledonian orogeny in the region [20,21,22,26,27]. The Indosinian movements caused the coalfield uplift, resulting in weathering and erosion of the Triassic strata. The magmatic activities consisted of the Indosinian lamprophyre and Yanshanian diabase invasions in the coalfield area [20,21,22,26,27]. A series of reverse faults was developed on the southern and southeastern margins of the basin including from north to south in the Qingciyao Fault, Wangjiayuan Fault, Meiyukou Fault, and Emaokou Fault. These faults probably provided channels for hydrothermal injections into the coal-bearing deposits [20,21,22,26,27]
The sedimentary sequence in the Jurassic coal-bearing strata of the Datong Coalfield mainly includes the Lower Jurassic Yongdingzhuang Formation, Middle Jurassic Datong Formation, and Middle Jurassic Yungang Formation [20,21,22]. The Datong Formation, the major coal-bearing unit in this area, contains several types of rocks including the conglomerate, gritstone, sandstone, medium sandstone, fine sandstone, and siltstone (Figure 2) [20,21,22]. In addition, it contains eight mineable coal seams, identified as Nos. 2, 3, 7, 10, 11, 12, 14, and 15. The coal-bearing sequence of the Datong Formation has the total thickness of 235 m (Figure 2) and is dominated by the fluvial and lacustrine sedimentary environment [20,21,22]. The No.12 coal seam is stable and widely distributed throughout the Datong Coalfield. The thickness of No.12 coal seam ranges from 0.35 to 7.90 m, with an average of 2.80 m [20,21,22]. The roof and floor samples in No.12 coal seam are characterized by fine sandstone and siltstone, respectively (Figure 2) [20,21,22].

3. Samples and Analytical Procedure

The collected samples were placed in a grinder whose material is hadifield steel for pulverization, and the pulverized samples were screened by 18–40 mesh and 200 mesh sieves, respectively. The screened samples were immediately placed in a plastic bag and sealed. After a sample was ground, the grinder and sieve were washed with distilled water and then dried, in order to avoid contaminating other samples. The sample crushing was performed at the Beijing Key Laboratory of Unconventional Natural Gas Geological Evaluation and Development Engineering of China University of Geosciences (Beijing).
Proximate analyses of the coals, including moisture, ash yield, volatile matter, total sulfur, and forms of sulfur were performed based on ASTM (American Society for Testing and Materials) Standards D3173-11, D3174-11, D3175-11, D3177-02, and D2492-02, respectively [28,29,30,31,32].
The mineralogical composition was determined by microscopy (Leica DM 2500P microscope by Leica Microsystems, Solms, Germany). Low-temperature ashing of coal was performed on an EMITECH K1050 plasma asher (Quorum, Ashford, UK), with the temperature maintained at less than 150 °C. X-ray diffraction (XRD) analyses of the low-temperature ashes were performed with Ni-filtered Cu-Kα radiation and a scintillation detector. The XRD patterns were recorded over a 2θ interval from 2.5–70°, with a step size of 0.01°. In order to determine the mineral composition from the X-ray diffractograms, the Siroquant™ commercial interpretation software developed by Taylor was used [33]. Further details of this technique have been provided by Ward and Ruan and Ward [34,35,36].
Coal samples of 80-mesh particle size were used for analysis of the mineralogical composition. A scanning electron microscope (HITACHI UHR FE-SEM, SU8220, HITACHI, Tokyo, Japan) equipped with an energy-dispersive X-ray spectrometer (SEM-EDS) was used to study the mineral distribution as well as the distribution patterns of several elements of interest in the coal.
Portions of all 15 samples were crushed into 200 mesh prior to elemental analysis. The 200 mesh samples were heated to 815 °C to create high-temperature ashes, which were then formed into tablets and measured via X-ray fluorescence spectrometry (XRF) (Thermo ADVANT XP+, Thermo Fisher Scientific, Waltham, MA, USA). All the residues were used to determine the contents of major element oxides (SiO2, TiO2, Al2O3, Fe2O3, MgO, CaO, MnO, Na2O, K2O, and P2O5). Trace elements, including REY (rare earth elements and yittrium), except for As, Se, Hg, and F, were determined via inductively coupled plasma mass spectrometry (ICP-MS) [37]. For ICP-MS, 200-mesh samples were digested using an UltraClave Microwave High Pressure Reactor (Milestone, Sorisole, Italy). The basic load for the digestion tank was composed of 330 ml distilled H2O, 30 ml 30% H2O2, and 2 ml 98% H2SO4. The initial nitrogen pressure was set to 50 bar, the highest temperature was set to 240 °C, and the digestion process lasted for 75 min. The reagents for the 50 mg sample digestion were 5 ml 40% HF, 2 ml 65% HNO3, and 1 ml 30% H2O2. Multi-element standards (Inorganic Ventures: CCS-1, CCS-4, CCS-5, and CCS-6) were used for the calibration of trace element concentrations [37]. Arsenic and Se were analyzed via ICP-MS with collision/reaction cell technology (ICP-CCT-MS) [38]. Fluorine was determined via pyrohydrolysis combined with an ion selective electrode (ISE) based on the ASTM method [39]. Mercury was determined using a Milestone DMA-80 Hg analyzer (with a 0.005-ng detection limit) (Milestone, Sorisole, Italy) [40].
The quantitative analyses of minerals and determinations of elements were completed at the State Key Laboratory of Coal Resources and Safe Mining of China University of Mining and Technology (Beijing, China).

4. Results

4.1. Proximate Analysis

Table 1 summarizes the results of total sulfur content and proximate analysis for the No.12 coal from the Tongjialiang mine in Datong Coalfield. According to the Chinese National Standards GB/T15224.1 [41] and 2 [42], MT/T 849 [43] and MT/T 850 [44], the No.12 coal is characterized by low ash (3.63–34.29%, mean 9.79%), low moisture (1.3–2.58%, mean 2.23%), medium volatile (14.1–39.67%, mean 20.98%) and ultra-low sulfur (0.13–0.33%, mean 0.25%) coals. The content of volatile matter in No.12 coal indicates that it is a low-medium volatile bituminous coal based on ASTM Standard D388-15, 2015 [45]. The total sulfur consists of inorganic sulfur (including pyritic sulfur and sulfate sulfur) and organic sulfur, and pyritic sulfur is a dominant form in all the samples. The percentage of total sulfur is low (<1%), which indicates that total sulfur is mainly derived from coal-forming plants [46].

4.2. Geochemistry

4.2.1. Major Elements

As shown in Table 2, the Tongjialiang coals have slightly higher average percentages of MgO (mean 0.38%) and P2O5 (mean 0.11%), and lower average percentages of the other major oxides, including SiO2 (mean 5.44%), TiO2 (mean 0.04%), Al2O3 (mean 1.54%), Fe2O3 (mean 1.28%), CaO (mean 0.64%), MnO (mean 0.01%), Na2O (mean 0.03%), and K2O (mean 0.05%), compared with Chinese coals reported by Dai et al. [3]. Due to the low ash yield, the Tongjialiang coals have relatively low average percentages of all the major oxides when converted to a whole-coal basis. SiO2 and Al2O3 are the major oxides in all the samples, although high proportions of Fe2O3 occur in samples TJL12-13 and TJL12-14.
SiO2/Al2O3 ratios for the samples (mean 4.06) are distinctly higher than the theoretical ratios for kaolinite (1.18) and Chinese coals (1.42). Therefore, a large amount of quartz is likely present in the mineral matter. Aluminum and Ti are regarded as essentially immobile elements due to the low solubility of their oxides and hydroxides in low temperature aqueous solutions [47]. Therefore, the ratios of Al2O3 and TiO2 should be close to the characteristics of their source rocks [47,48]. Al2O3/TiO2 ratios for the coal bench samples range from 20.63 to 86.62 with an average of 41.20.

4.2.2. Trace Elements

The concentrations of trace elements (on an ash basis) in Tongjialiang coals, parting, and floor samples are listed in Table 3, along with the concentration coefficients (CC = the ratio of average elemental concentrations (on an ash basis) in the investigated coal/the average concentrations in World hard coals (on an ash basis)) [49]. Based on the relative enrichment of elements, the CC value can be divided into six categories: unusually enriched (CC > 100), significantly enriched (10 < CC < 100), enriched (5 < CC < 10), slightly enriched (2 < CC < 5), normal (0.5 < CC < 2), and depleted (CC < 0.5) [49].
As shown in Figure 3, compared with the World hard coals reported by Ketris and Yudovich [50], Be (48.47 μg/g), Cr (235.23 μg/g), Co (145.71 μg/g), Ni (346.83 μg/g), Ge (278.48 μg/g), Sn (62.27 μg/g), Ta (13.22 μg/g), and W (23.91 μg/g) are slightly enriched in the Tongjialiang coals. The concentrations of Li (101.15 μg/g), F (851.45 μg/g), Sc (17.67 μg/g), V (221.32 μg/g), Cu (45.86 μg/g), Ga (22.69 μg/g), Se (4.12 μg/g), Sr (528.96 μg/g), Zr (446.06 μg/g), Nb (26.00 μg/g), Hf (12.55 μg/g), Pb (41.46 μg/g), Th (11.86 μg/g), and U (7.66 μg/g) are close to the average values of the world’s hard coals. Additionally, all the remaining elements are depleted in the Tongjialiang coals.

4.2.3. Rare Earth Elements

In this study, a threefold geochemical classification of rare earth elements and yttrium (REY) was used. Based on Seredin-Dai’s classification [51], the REYs are divided into three types: light (LREY including La, Ce, Pr, Nd, and Sm), medium (MREY including, Eu, Gd, Tb, Dy, and Y), and heavy (HREY including, Ho, Er, Tm, Yb, and Lu). The concentrations and geochemical parameters of REY in No.12 coal are listed in Table 4. The concentration of REY in the coal ash samples ranges from 14.87 μg/g to 1172.47 μg/g, with an average of 399.70 μg/g, which is much lower than corresponding value for the world’s hard coals (445.3 μg/g) [50]. The content of LREE (9.09–1049.23 μg/g, mean 303.75 μg/g) is much higher than that of MREE (4.94–199.03 μg/g, mean 80.69 μg/g) and HREE (0.85–48.83 μg/g, mean 15.26 μg/g).
Compared with the Upper Continental Crust (UCC) [52], three types of coal benches are identified as: L-type (LREY; LaN/LuN > 1), M-type (MREY; LaN/SmN < 1, GdN/LuN > 1), and H-type (HREY; LaN/LuN < 1) [53]. The REY enrichment patterns of the Tongjialiang coals are shown in Figure 4. The samples of TJL12-4, TJL12-5 and TJL12-10, are characterized as L-type enrichment as well as one parting sample (TJL12-8p) and one floor sample (TJL12-15f). The H-type enrichment patterns include six coal bench samples, namely, TJL12-1, TJL12-2, TJL12-3, TJL12-9, TJL12-12, and TJL12-14. The samples of TJL12-6, TJL12-11, and TJL12-13 belong to the M-H type enrichment. Only sample TJL12-7 is characterized by L-M type enrichment.
Yan et al. reported that positive Eu anomalies could be caused by overestimation of Eu during ICP-MS analysis due to interference from BaO or BaOH [54]. If Ba/Eu > 1000, the interfered Eu is highly elevated. Therefore, when samples contain Ba/Eu less than 1000, the interference of Ba on Eu can be ignored. Despite the positive correlation between Ba and Eu concentrations (r = 0.80), lower Ba/Eu values (468.38 on an average) in the investigated samples indicate that the positive Eu anomalies in these samples are not caused by the interference of Ba. All the coal samples are characterized by weakly positive or no pronounced Eu anomalies (δEu = EuN/EuN * = EuN / (0.67 × SmN + 0.33 × TbN) ranging from 0.58–1.28, with an average of 0.90) [53].

4.3. Abundances and Occurrence Modes of Minerals

Table 5 lists the proportion of minerals in the coal LTAs (low temperature ashes), partings, roof, and floor samples identified by LTA-XRD and Siroquant. The mineralogical composition of the coal samples is mainly characterized by quartz, kaolinite, pyrite, siderite, and ankerite, while illite, I/S, calcite, rutile, anorthite, goyazite, and basanite are less abundant. Figure 5 shows the vertical variations of the contents of low temperature ashes and minerals in LTAs in the No.12 coal.

4.3.1. Oxide Minerals

Quartz (ranging 0.5% to 75.1%, mean 45.62%) makes up a large percentage of minerals in the coal benches. The content of quartz in the upper benches is higher than that in the lower benches (Figure 5). The quartz in coals is present as infillings in maceral cells and as disseminated particles in macerals and kaolinite matrix. The presence of some angular shaped quartz particles (10–20 μm) (Figure 6A,B) indicates that quartz has a detrital origin and was transported over a short distance from the sediment source region which is the Yinshan Upland located to the north of the Datong Coalfield [55,56]. In most cases, the quartz occurs as either fine quartz (less than 5 μm) (Figure 6C–E) disseminating in macerals, or as infillings in maceral cells, indicating an authigenic origin [55,56]. As previously reported, the Yinshan Upland also served as the sediment source region for the Hailiushu Coalfield, Heidaigou Coalfield, and Adaohai Coalfield [57,58,59]. The content of quartz in the Tongjialiang coals is significantly higher than that in the Heidaigou coals (ranging from bdl–16.4%, mean 2.5%), Hailiushu coals (ranging from 0.2–9.6%, mean 1.97%) and Dantanhao coals (bdl–38.2%, mean 13.03%), respectively [57,58,59].
Under SEM-EDS, rutile was occasionally observed in some coal bench samples (Figure 6F). It occurs as disseminated particles, indicating a syngenetic origin.

4.3.2. Clay Minerals

Kaolinite is another dominant mineral in coal benches, ranging from bdl to 46.1%, with an average of 28.38%. The contents of kaolinite in parting sample (85.2%) and floor sample (43.4%) are higher than those in coal benches (Figure 5). Kaolinite mainly occurs as lens-shaped particles (Figure 7A,B) and thin-layers (Figure 7C,D) distributed along the bed plane, indicating detrital materials of terrigenous origin. In addition, a portion of kaolinite filling in maceral cells (Figure 7E,F) indicates formation by authigenic processes [11,12]. In a few cases, kaolinite occurs as infillings in maceral fracture (Figure 7G), suggesting an epigenetic origin [11,12]. The Tongjialiang coals have higher kaolinite content than Heidaigou coals (ranging from 3.6–19.5%, mean 9%). However, they have lower kaolinite content than both Hailiushu coals (85–98.5%, mean 95.6%) and Datanhao coals (ranging from 13–96.8%, mean 76.26%) [57,58,59].
In addition to the TJL12-15f sample, the proportion of illite in most samples is low, and may be below the detection limit of the XRD and Siroquant techniques. However, illite is also occasionally observed in some samples under SEM. Illite is considered to be formed due to the weathering of feldspar and mica in the sediment source region [11,12]. During the peat accumulation period and the early diagenesis stage, illite was transported to the peat swamp. Illite in No.12 coal disseminates in the maceral and kaolinite matrix, indicating a syngenetic origin (Figure 7I).

4.3.3. Sulfide Minerals

Pyrite is observed and detected in most coal bench samples, and its content ranges from bdl to 2.9%, with an average of 1.25%. Pyrite is distributed as massive forms in the organic matrix (Figure 8A), as disseminated particles in macerals (Figure 8A) and, in a few cases, as infillings (Figure 8B) in maceral-fractures. It can be deduced that pyrite of massive forms and disseminated particles is from a syngenetic origin [11,12,60,61]. The fracture-filling pyrite is likely deposited from migrating solutions, suggesting an epigenetic origin [11,12,60,61].

4.3.4. Carbonate Minerals

In all the coal bench samples, the content of siderite ranges from bdl to the maximum value of 79.4% in sample TJL12-14, with an average of 14.35%. The proportion of siderite is significantly higher in lower benches (especially in TJL12-13 and TJL12-14) than upper benches (Figure 5). Two modes of occurrence are observed for siderite in coals: coarse-grained massive siderite (Figure 9A) and cell-filling siderite (Figure 9B). The massive siderite is of a syngenetic origin and the cell-filling siderite is probably of an authigenic origin [11,12].
Ankerite in the coal LTA residues varies from 0.5% to 38.2%, with an average of 10.22. The proportion of ankerite is higher in the LTA of coal samples TJL12-7 and TJL12-9 compared with the other coal benches. SEM-EDS observation shows that ankerite occurred as cell-fillings (Figure 9C,D), vein and (Figure 9E) fracture-fillings (Figure 9F). These modes of occurrence indicate that ankerite in the Tongjialiang coals is probably of an epigenetic origin [12,62].
The content of calcite in the coal LTAs is low. Calcite is only detected in samples TJL12-4, TJL12-6, TJL12-7, and TJL12-14 by XRD and Siroquant techniques. SEM-EDS observation shows that calcite occurs as cell-infillings, indicating an authigenic origin (Figure 8G,H) [11,12,62].

5. Discussion

5.1. Sediment Source Region

The different ratios of Al2O3/TiO2 represent different types of sediment source rocks, indicating, in particular, the sediment-source regions for coal deposits [47,48,63]. Ratios of Al2O3/TiO2 ranging from 3 to 8 indicate mafic source rocks, 8–21 for intermediate source rocks, and 21–70 for felsic source rocks [47,48]. Al2O3/TiO2 ratios for the coal bench samples range from 20.63 to 86.62 with an average of 41.20, indicating that the sediment-source region for the coal and its host rocks is mainly characterized by felsic and intermediate source rocks.
The dominant sediment source of the Jurassic coals from the Datong Coalfield is generally considered to be gneiss and granite of the Yinshan Upland, which is typically enriched in lithophile elements such as Li, Be, F, Ga, Zr, Nb, Hf, Ta, Th, U, etc. [22]. A number of studies have indicated that the coals with sediment source consisting of felsic rocks have high concentration of lithophile elements [57,64]. The Al2O3/TiO2 ratios indicate that the sediment-source region for the coals and the host rocks is mainly characterized by felsic and intermediate source rocks, corresponding to the characteristics of the gneiss of the Yinshan Upland. In the No.12 coal samples, some lithophile elements, including Li, Be, F, Zr, Nb, Hf, Ta, and W show slightly higher concentrations. Furthermore, some siderophile elements, including V, Cr, Co, Ni, Ge, and Sn, are also slightly enriched in the No.12 coal. This may be attributed to the fact that the No.12 coal mainly originated from felsic detrital materials, and to a lesser extent, from the mafic detrital materials.
Eu anomalies are generally considered to originate from the sediment source region. The ratios of Al2O3/TiO2 indicate that the sediment source region of the No.12 coal is characterized by source rocks with felsic and intermediate compositions. Coals with input from felsic and felsic-intermediate detrital materials usually display distinctly negative Eu anomalies [53]. Dai et al. reported that the detrital input of alkali mafic rocks and high-temperature solutions could cause positive Eu anomalies in coals [53]. The L-type enrichment generally reflects a terrigenous origin [51]. The samples of TJL12-4, TJL12-5, TJL12-8p, and TJL12-10, are characterized by L-type REY enrichment patterns, indicating that these samples may originate from the detrital materials of the sediment source region. Furthermore, these samples display no pronounced or weakly negative Eu anomalies. Hence, it can be deduced that these samples may have originated largely from felsic detrital materials and, to a lesser extent, from mafic detrital materials. This may be due to the fact that the mafic detrital materials are characterized by positive Eu anomalies which would overprint the negative Eu anomalies caused by input of felsic detrital materials [51,53]. The floor sample TJL12-15f is characterized by the L-type REY enrichment pattern and Al2O3/TiO2 ratio of 33.06, indicating that the floor sample is probably derived from felsic source rocks. However, this floor sample displays weakly positive Eu anomaly rather than negative Eu anomaly as expected. The weakly positive Eu anomalies are possibly due to the high content of plagioclase and other feldspars in the granite from the sediment source region resulting from magmatic fractionation or from gravitational separation during the sedimentary processes [65]. Generally, Eu is concentrated in the feldspar of granite, especially in the plagioclase [65]. Therefore, the source rock of the floor sample TJL12-15f is characterized by weakly positive Eu anomalies because a high content of plagioclase was retained in the granite from the sediment source region.
In addition, the formation of syngenetic siderite in No.12 coal is related to the weathering of biotite in the sediment source region [22]. A large proportion of Fe2+ was released by the weathering of biotite in the gneiss of the Yinshan Upland [22]. Subsequently, the Fe-rich water entered into the paleomire where the weakly acidic or weakly alkaline conditions developed. Due to the low sulfur content, Fe2+ preferentially combined with CO2 released by organic matter to form a large amount of the syngenetic siderite [11,12,66]. Siderite is typically formed when the supply of sulfate ions for bacterial reduction is limited [11,12,66,67]. As indicated by Ward, abundant syngenetic siderite usually indicates deposition of coal under non-marine conditions, or under the influence of low sulfate water in the paleomire [11,12].

5.2. Injection of Low Temperature Hydrothermal Fluids

The modes of occurrence of the epigenetic ankerite provide further evidence that there may be injection of low temperature hydrothermal fluids into the paleomire [11,12,62,68]. As discussed above, ankerite that occurs as veins, cell infillings, and fracture infillings can be considered to be precipitated from Fe-Mg-Ca rich low temperature hydrothermal fluids circulating in the coal seams in the late stage of diagenesis [11,12,62,69]. Although some lithophile elements show enrichment, Ta and W are more enriched than the other lithophile elements in No.12 coal. The correlation coefficients of Ta-ankerite and W-ankerite are 0.76 and 0.75 (Figure 10), respectively, indicating that a portion of Ta and W in No.12 coal may be derived from the Fe-Mg-Ca rich low temperature hydrothermal fluids.
Furthermore, it is noteworthy that the siderite is replaced by ankerite in some samples (Figure 11). This is probably because when the hydrothermal fluid invaded into the coal seam in the later diagenesis stage, some epigenetic ankerite was formed as a product of metasomatism between syngenetic siderite and Fe-Mg-Ca rich hydrothermal fluids.
Dai et al. reported that the positive Eu anomaly would be expected to be strongly positive due to the injection of high-temperature hydrothermal solutions (>200 °C) coupled with an extremely reducing environment [53]. Previous investigation by Dai et al. shows that strong positive Eu anomalies in Hongmao Coalfield, Yishan Coalfield, and Luocheng Coalfield from Guangxi Province resulted from the injection of high-temperature hydrothermal solutions [40,70]. However, in the present study, the samples with the H-type and M-H type enrichment patterns show no pronounced and weakly positive Eu anomalies, indicating that the temperature of the hydrothermal fluids circulating in the basin may be relatively low (< 200 °C) [51,53].
The H-type enrichment is probably due to the natural waters enriched in HREY that may circulate in coal basins. The natural waters include marine waters, alkaline terrestrial waters, some cold mineral waters, some low-temperature (130 °C) alkaline hydrothermal solutions, and high-temperature (>500 °C) volcanogenic fluids [51]. The formation of Jurassic coals from Datong Coalfield was affected by fresh water [22,69]. Furthermore, the epigenetic ankerite which is derived from the alkaline low temperature hydrothermal fluids is observed in the No.12 coal. No evidence that the HREE enrichment was influenced by the alkaline terrestrial waters, cold mineral waters and high-temperature (>500 °C) volcanogenic fluids is observed in the coals of present study. Therefore, it is believed that the alkaline low temperature hydrothermal fluids may be responsible for the HREE enrichment. This may be due to the fact that the Jurassic coal seams were invaded by the Yanshanian diabase which may be considered as the source of the alkaline low temperature hydrothermal fluids [22]. Additionally, some siderophile elements, such as V, Cr, Co, Ni, Ge, and Sn, show significantly higher concentrations in sample TJL12-1 than other samples. The sample TJL12-1 characterized by weakly positive Eu anomaly and H-type enrichment pattern is probably influenced by the injection of low temperature hydrothermal solutions, which may be the reason for the enrichment of V, Cr, Co, Ni, Ge, and Sn.
The M-type enrichment is possibly related to acidic natural waters that may circulate in coal basins, including acidic hydrothermal solutions with high REY concentrations [51,71]. Another reason for an M-type enrichment pattern in coals may be the higher sorption of MREY by humic matter in comparison with that of LREY and HREY [51]. As discussed above, the M-H type enrichment is generally attributed to the alkaline low temperature hydrothermal solutions circulating in the basin. It is also ascribed, to a lesser extent, to the acidic hydrothermal fluids and the humic matter in the coals.

6. Conclusions

The Middle Jurassic No.12 coal from the Tongjialiang Mine is determined to be a low-medium volatile bituminous coal characterized by low ash yield content, low moisture content, and ultra-low sulfur content. Compared with Chinese coals, the Tongjialiang coals have slightly higher average percentages of MgO and P2O5, and lower average percentages of the other major oxides, including SiO2, TiO2, Al2O3, Fe2O3, CaO, MnO, Na2O, and K2O. Compared with the world’s hard coals, Be, Cr, Co, Ni, Ge, Sn, Ta, and W are slightly enriched in Tongjialiang coals. The concentrations of Li, F, Sc, V, Cu, Ga, Se, Sr, Zr, Nb, Hf, Pb, Th, and U are close to the average values of the these elements in the worold’s hard coals. The minerals in No.12 coal mainly include quartz, kaolinite, siderite, and ankerite, along with a small proportion of pyrite, illite, calcite, and rutile. The modes of occurrence of quartz indicate authigenic and terrigenous origins. Kaolinite has a variety of origins such as authigenic, terrigenous, and epigenetic origins. Siderite, pyrite, calcite, and rutile are probably of syngenetic origins. Ankerite occurs as veins, cell-infillings, and fracture-infillings, indicating an epigenetic origin. The formation of syngenetic siderite in No.12 coal is related to the weathering of biotite in the gneiss of the Yinshan Upland. The modes of occurrence of ankerite indicate that the coals may be affected by the injection of low temperature hydrothermal fluids. Interestingly, a portion of epigenetic ankerite is a product of metasomatism between syngenetic siderite and the epigenetic Fe-Mg-Ca rich hydrothermal fluids.
Based on the ratios of Al2O3/TiO2, L-type REY enrichment patterns as well as some enriched lithophile elements and siderophile elements, the sediment source rocks are expected to be mainly from the felsic detrital materials and from the mafic detrital materials to a lesser extent. In addition, the H and M-H type REY enrichment patterns as well as the modes of occurrence of ankerite indicate that the No.12 coal was also influenced by the injection of low temperature hydrothermal fluids into the coal seams.

Author Contributions

Y.Y. designed the experiments and performed both SEM-EDS and XRD. S.T. guided the experiments and analyzed the data. S.Z. analyzed the experimental data. Y.Y. wrote the bulk of this paper. All authors participated in writing this paper.

Funding

This research was funded by the National Key Basic Research Program of China (no. 2014CB238901) and the Key Program of the National Natural Science Foundation of China (no. 41330317).

Acknowledgments

We are particularly grateful for the anonymous reviewers for providing useful suggestions and comments.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. The location and geological map of the Datong Coalfield.
Figure 1. The location and geological map of the Datong Coalfield.
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Figure 2. General stratigraphic sequence of the Datong Formation from the Datong Coalfield.
Figure 2. General stratigraphic sequence of the Datong Formation from the Datong Coalfield.
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Figure 3. Concentration coefficients of trace elements in the No.12 coal, normalized by average concentrations in the world’s hard coals.
Figure 3. Concentration coefficients of trace elements in the No.12 coal, normalized by average concentrations in the world’s hard coals.
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Figure 4. REY distribution patterns in the coal benches, roof, floor and partings, normalized to the upper continental crust (UCC) reported by Taylor and McLennan [52]; (A) pattern of H-type in coal benches; (B) pattern of L type in coal benches; (C) pattern of M-H type in coal benches; (D) pattern of L-M type in coal benches; (E) pattern of L-type in the floor and parting samples.
Figure 4. REY distribution patterns in the coal benches, roof, floor and partings, normalized to the upper continental crust (UCC) reported by Taylor and McLennan [52]; (A) pattern of H-type in coal benches; (B) pattern of L type in coal benches; (C) pattern of M-H type in coal benches; (D) pattern of L-M type in coal benches; (E) pattern of L-type in the floor and parting samples.
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Figure 5. Vertical variations of low temperature ash yield and minerals in LTA and rock samples in the No.12 coal from the Tongjialiang mine.
Figure 5. Vertical variations of low temperature ash yield and minerals in LTA and rock samples in the No.12 coal from the Tongjialiang mine.
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Minerals 09 00184 g006 550
Figure 6. Oxide minerals in the No.12 coal, (A) Quartz disseminated in macerals (reflected light); (B) Quartz disseminated in kaolinite matrix (reflected light); (C) Quartz filled in maceral-cells (SEM, secondary electron image); (D) Quartz disseminated in macerals (SEM, secondary electron image); (E) Quartz disseminated in macerals (SEM, secondary electron image); (F) Rutile disseminated in macerals and kaolinite matrix (SEM, secondary electron image).
Figure 6. Oxide minerals in the No.12 coal, (A) Quartz disseminated in macerals (reflected light); (B) Quartz disseminated in kaolinite matrix (reflected light); (C) Quartz filled in maceral-cells (SEM, secondary electron image); (D) Quartz disseminated in macerals (SEM, secondary electron image); (E) Quartz disseminated in macerals (SEM, secondary electron image); (F) Rutile disseminated in macerals and kaolinite matrix (SEM, secondary electron image).
Minerals 09 00184 g006
Minerals 09 00184 g007a 550Minerals 09 00184 g007b 550
Figure 7. Clay minerals in No.12 coal, (A) lens-shaped kaolinite distributed along the bedding plane (reflected light); (B) lense-shaped kaolinite distributed along the bedding plane (SEM, secondary electron image); (C) thin-layer kaolinite distributed along the bedding plane (reflected light); (D) thin-layer kaolinite distributed along the bedding plane (SEM, secondary electron image); (E) cell-infilling kaolinite in macerals (SEM, secondary electron image); (F) cell-infilling kaolinite in fusinite (reflected light); (G) kaolinite fills in fracture (SEM, secondary electron image); (H) energy dispersive X-ray spectrometry (EDS) of kaolinite; (I) illite (SEM, secondary electron image); (J) energy dispersive X-ray spectrometry (EDS) of illite.
Figure 7. Clay minerals in No.12 coal, (A) lens-shaped kaolinite distributed along the bedding plane (reflected light); (B) lense-shaped kaolinite distributed along the bedding plane (SEM, secondary electron image); (C) thin-layer kaolinite distributed along the bedding plane (reflected light); (D) thin-layer kaolinite distributed along the bedding plane (SEM, secondary electron image); (E) cell-infilling kaolinite in macerals (SEM, secondary electron image); (F) cell-infilling kaolinite in fusinite (reflected light); (G) kaolinite fills in fracture (SEM, secondary electron image); (H) energy dispersive X-ray spectrometry (EDS) of kaolinite; (I) illite (SEM, secondary electron image); (J) energy dispersive X-ray spectrometry (EDS) of illite.
Minerals 09 00184 g007aMinerals 09 00184 g007b
Minerals 09 00184 g008 550
Figure 8. Pyrite in the No.12 coal, (A) pyrite as massive forms distributed in the macerals (reflected light); (B) Pyrite disseminated in macerals (reflected light).
Figure 8. Pyrite in the No.12 coal, (A) pyrite as massive forms distributed in the macerals (reflected light); (B) Pyrite disseminated in macerals (reflected light).
Minerals 09 00184 g008
Minerals 09 00184 g009 550
Figure 9. Carbonate minerals in No.12 coal: (A) siderite fills in maceral-cells (SEM, secondary electron image); (B) siderite occurs as coarse-grained massive (SEM, secondary electron image); (C) ankerite fills in maceral-cells (SEM, secondary electron image); (D) ankerite fills in maceral-cells (SEM, secondary electron image); (E) ankerite occurs as veins (SEM, secondary electron image); (F) ankerite fills in maceral-fracture (SEM, secondary electron image); (G) calcite fills in maceral cells (SEM, secondary electron image); (H) calcite fills in maceral cells (SEM, secondary electron image).
Figure 9. Carbonate minerals in No.12 coal: (A) siderite fills in maceral-cells (SEM, secondary electron image); (B) siderite occurs as coarse-grained massive (SEM, secondary electron image); (C) ankerite fills in maceral-cells (SEM, secondary electron image); (D) ankerite fills in maceral-cells (SEM, secondary electron image); (E) ankerite occurs as veins (SEM, secondary electron image); (F) ankerite fills in maceral-fracture (SEM, secondary electron image); (G) calcite fills in maceral cells (SEM, secondary electron image); (H) calcite fills in maceral cells (SEM, secondary electron image).
Minerals 09 00184 g009
Minerals 09 00184 g010 550
Figure 10. Correlation of: (A) Ta to ankerite and (B) W to ankerite.
Figure 10. Correlation of: (A) Ta to ankerite and (B) W to ankerite.
Minerals 09 00184 g010
Minerals 09 00184 g011 550
Figure 11. (A–D) Epigenetic ankerite was formed due to the metasomatism between syngenetic siderite and Fe-Mg-Ca rich hydrothermal fluids (SEM, secondary electron image).
Figure 11. (A–D) Epigenetic ankerite was formed due to the metasomatism between syngenetic siderite and Fe-Mg-Ca rich hydrothermal fluids (SEM, secondary electron image).
Minerals 09 00184 g011
Table
Table 1. Bench thickness (cm), proximate, and forms of sulfur (%) of No.12 coal samples from the Tongjialiang Mine.
Table 1. Bench thickness (cm), proximate, and forms of sulfur (%) of No.12 coal samples from the Tongjialiang Mine.
SampleThicknessMadAdVdafSt.dSp.dSs.dSo.d
TJL12-1152.224.122.750.330.190.010.13
TJL12-2152.2314.3823.090.330.280.010.04
TJL12-3152.126.7918.580.250.240.010.00
TJL12-4152.584.7819.780.250.220.010.02
TJL12-5152.165.0815.730.310.280.010.02
TJL12-6152.513.6320.970.290.250.010.03
TJL12-7102.584.7625.260.250.180.010.06
TJL12-8p100.7785.3673.090.080.080.000.00
TJL12-9102.215.7114.10.190.140.000.05
TJL12-10152.347.1516.290.210.160.010.04
TJL12-11152.474.1723.650.270.130.010.13
TJL12-12202.1711.8116.350.290.140.010.14
TJL12-13202.110.5616.570.190.140.010.04
TJL12-14201.334.2939.670.130.120.010.00
TJL12-15f100.7388.978.580.050.040.010.00
AVE-2.239.7920.980.250.190.010.05
M, moisture; A, ash yield; V, volatile matter; ad, air-dry basis; d, dry basis; daf, dry and ash-free basis; St, total sulfur; Sp, pyritic sulfur; Ss, sulfate sulfur; So, organic sulfur.
Table
Table 2. Concentrations of major oxides in Tongjialiang coal (%) (on a whole-coal basis).
Table 2. Concentrations of major oxides in Tongjialiang coal (%) (on a whole-coal basis).
SampleLOISiO2TiO2Al2O3Fe2O3MgOCaOMnONa2OK2OP2O5SiO2/Al2O3Al2O3/TiO2
TJL12-195.93.200.020.480.110.030.080.0010.020.020.056.63 20.36
TJL12-285.6211.600.042.350.130.050.030.0010.020.110.014.93 56.19
TJL12-393.215.360.031.130.080.050.070.0010.020.050.044.74 44.49
TJL12-495.223.600.030.680.070.100.09bdl0.070.030.065.26 23.46
TJL12-594.924.290.030.660.020.010.010.0000.010.020.036.54 24.09
TJL12-696.372.600.030.680.030.020.120.0000.010.030.103.79 22.93
TJL12-795.241.350.010.830.480.480.990.0040.010.040.081.62 70.93
TJL12-8p14.6442.730.5935.592.231.191.370.0090.220.820.181.20 60.32
TJL12-984.2911.550.043.580.090.110.130.0010.050.120.083.23 86.62
TJL12-1092.855.180.021.370.110.050.110.0010.010.050.183.79 56.37
TJL12-1195.832.650.030.850.150.030.200.0010.010.030.203.12 25.17
TJL12-1288.196.450.083.120.780.310.730.0040.020.080.012.07 38.57
TJL12-1389.445.140.041.103.140.220.460.0310.020.010.284.66 27.16
TJL12-1465.717.700.083.1911.443.435.280.1090.080.030.342.41 39.28
TJL12-15f11.153.270.8828.950.920.630.150.0040.103.610.161.84 33.06
AVE90.215.440.041.541.280.380.640.010.030.050.114.0641.20
Chinese coal-8.470.335.984.850.221.230.0150.160.190.091.4218.12
bdl: below detetion limit.
Table
Table 3. Concentrations of trace elements in the No.12 coal from the Tongjialiang mine (μg/g) (on an ash basis).
Table 3. Concentrations of trace elements in the No.12 coal from the Tongjialiang mine (μg/g) (on an ash basis).
SampleLiBeFScVCrCoNiCuZnGaGeAsSeRbSrZr
TJL12-184.18235.02521.1176.172585.851065.64502.391030.3898.87657.3391.96551.465.904.2022.55257.471219.75
TJL12-2105.8641.66454.5714.9240.70137.07164.64192.8128.71bdl23.1920.882.763.6616.75146.20229.11
TJL12-395.0527.43293.477.1025.6792.41147.33181.8634.7196.2313.1112.502.040.259.92204.48182.04
TJL12-441.4256.10316.044.7828.17641.20405.62681.0367.58bdl18.1139.95bdlbdlbdl385.29139.32
TJL12-5128.6045.05784.9745.4814.04193.26138.47282.1840.36bdl17.7515.98bdl3.9376.691169.27197.72
TJL12-648.8386.821261.289.2936.07275.59246.34599.02111.51bdl24.4748.333.657.12bdl631.79126.69
TJL12-725.8366.41888.5314.5421.4751.87107.92457.1132.89bdl25.4915.28bdl5.721.94984.482336.15
TJL12-8p39.001.531058.771.7711.2412.461.2118.8511.4919.3135.104.740.820.369.99136.125.11
TJL12-9235.949.90620.908.4517.1658.496.1951.7417.88bdl12.92bdl0.643.3513.0796.05bdl
TJL12-1097.9923.381417.3013.9927.83132.0424.64196.4249.69bdl21.2512.163.3612.413.871218.38396.74
TJL12-1159.7824.992392.3614.3331.94160.4473.25499.5959.88bdl16.5022.399.203.56bdl906.16285.07
TJL12-12236.776.67493.6612.4834.5361.2518.34121.3724.03bdl17.462.1810.651.159.35193.50147.76
TJL12-1393.185.031411.026.6511.68119.5321.26107.3822.11bdl4.501.853.673.80bdl229.8479.54
TJL12-1461.571.63213.601.572.0969.2637.90107.847.9981.898.234.300.250.3011.62453.6112.87
TJL12-15f80.781.831272.035.78163.06210.9617.6162.6075.31134.9838.442.081.031.2587.41122.59163.99
AVE101.1548.47851.4517.67221.32235.23145.71346.8345.86278.4822.6962.273.834.1218.42528.96446.06
World 1821263024170822652741103618487.60110730230
CC 21.234.041.350.741.302.875.606.670.622.530.633.460.080.540.170.721.94
SampleNbMoCdInSnSbCsBaHfTaWHgTlPbBiThU
TJL12-179.84bdl2.080.051.162.460.72548.1823.86bdlbdl0.37bdl170.83bdl4.308.55
TJL12-217.002.570.220.084.170.281.46306.046.802.99bdl0.163.1237.31bdl12.986.08
TJL12-310.561.790.590.031.17bdl0.47354.994.81bdlbdl0.101.6436.88bdl4.725.08
TJL12-48.513.02bdl0.041.34bdlbdl2088.532.89bdlbdl0.08bdl17.82bdl0.844.36
TJL12-55.13bdl0.320.041.50bdl3.633587.734.46bdlbdl0.07bdl20.59bdl67.066.59
TJL12-610.4523.81bdl0.055.28bdlbdl1977.093.02bdlbdl0.11bdl25.13bdl9.4619.80
TJL12-7125.9721.95bdl0.08205.683.590.343469.3980.9958.2244.720.07bdl53.81bdl3.3413.86
TJL12-8p0.23bdl0.230.07bdlbdl1.77262.380.10bdl0.710.140.1652.941.2830.255.71
TJL12-9bdlbdl0.19bdlbdlbdl0.40232.01bdlbdlbdl0.050.2827.68bdl13.588.45
TJL12-1027.754.430.500.030.870.81bdl4367.229.87bdl0.220.07bdl61.75bdl6.2817.83
TJL12-1112.214.200.240.101.16bdlbdl3052.177.04bdl330.191.1669.96bdl5.453.96
TJL12-128.080.860.410.032.91bdl0.47263.174.543.56bdl0.070.835.52bdl18.123.08
TJL12-135.940.040.13bdl0.79bdlbdl1660.811.970.08bdl0.040.720.74bdl7.671.64
TJL12-140.602.430.130.010.27bdl0.691008.960.321.2417.690.020.0310.92bdl0.310.28
TJL12-15f15.882.500.460.111.950.117.84486.704.481.241.510.030.7950.200.196.163.00
AVE26.006.510.370.0418.861.780.821762.7912.5513.2223.910.111.1141.46bdl11.867.66
World 1 22141.100.11858980927.800.624.60384.30231.90
CC21.180.460.340.382.360.360.101.801.396.613.070.170.241.09bdl0.520.51
1 World’s hard coals reported by Ketris and Yodvich [50]; 2 CC = average concentrantion of the trace elements in coals (on an ash basis) vs. world’s hard coals (on an ash basis); bdl: below detection limit.
Table
Table 4. Concentration and geochemical parameters of REY in the No.12 coals (μg/g) (on an ash basis).
Table 4. Concentration and geochemical parameters of REY in the No.12 coals (μg/g) (on an ash basis).
ElementsTJL12-1TJL12-2TJL12-3TJL12-4TJL12-5TJL12-6TJL12-7TJL12-8pTJL12-9TJL12-10TJL12-11TJL12-12TJL12-13TJL12-14TJL12-15fAVE
La17.5322.0813.08189.71194.9676.1072.2443.715.32308.9559.305.5026.102.4948.1076.41
Ce43.9054.7536.47270.42559.35127.57133.2465.2010.50489.90157.2510.2549.794.23105.87149.82
Pr6.236.874.8426.5437.8313.4714.9210.671.1948.9121.661.035.580.4410.9314.58
Nd28.8826.4119.8094.54122.0952.1855.3335.995.10172.3487.294.2824.011.6439.6353.38
Sm8.025.924.0516.7318.0311.5511.375.631.4829.1211.341.325.100.296.499.56
Eu3.281.130.562.102.962.311.780.650.274.431.790.290.850.071.431.68
Gd12.946.944.2014.2521.9317.3214.794.642.5430.4112.641.804.670.396.2311.14
Tb3.331.050.590.962.372.691.940.430.582.721.350.200.490.050.751.41
Dy27.006.985.055.2814.7919.3612.221.614.7511.589.362.513.350.413.659.43
Y152.4844.9532.1831.4994.84126.7461.336.6928.3557.3772.4715.0920.114.0217.3057.03
Ho5.751.520.850.843.043.572.160.290.931.991.880.490.590.090.691.82
Er18.454.873.082.819.359.906.300.823.286.086.801.862.020.311.865.78
Tm2.560.730.350.291.461.100.760.120.450.870.920.250.250.050.270.77
Yb19.225.113.112.8111.608.476.470.873.386.957.292.252.380.351.636.11
Lu2.850.720.320.211.540.930.630.130.480.840.970.300.280.050.220.78
∑REY352.43190.02128.53658.971096.13473.27395.48177.4668.601172.47452.3147.43145.5614.87245.06399.70
∑LREY104.56116.0378.24597.93932.26280.87287.10161.2023.581049.23336.8422.39110.579.09211.02303.75
∑MREY199.0361.0642.5754.08136.89168.4292.0614.0236.49106.5197.6119.8829.474.9429.3680.69
∑HREY48.8312.947.726.9626.9823.9716.322.248.5416.7317.855.175.520.854.6715.26
LaN/LuN0.070.330.439.651.350.871.223.560.123.920.660.190.980.572.291.57
LaN/SmN0.330.560.481.701.620.990.951.170.541.590.780.630.771.281.110.94
GdN/LuN0.390.790.782.941.091.181.323.080.432.531.000.461.130.642.221.13
δEu1.280.900.700.800.860.840.750.690.580.880.851.090.951.181.200.90
TypeHHHLLM-HL-MLHLM-HHM-HHL-
N. values normalized by the average REY content of Upper Continental Crust. δEu = EuN/EuN* = EuN/(0.67 × SmN + 0.33 × TbN) [53].
Table
Table 5. Mineralogical compositions and contents of coal LTAs and non-coal samples in No.12 coal in the Tongjialiang Mine (%) (on an ash basis).
Table 5. Mineralogical compositions and contents of coal LTAs and non-coal samples in No.12 coal in the Tongjialiang Mine (%) (on an ash basis).
SamplesLTAQuartzKaoliniteIlliteI/SPyriteSideriteAnkeriteCalciteRutileAnorthiteGoyaziteBassanite
TJL12-18.161.430.4--1.74.22.3-----
TJL12-214.6366.432.3--0.40.40.5-----
TJL12-38.9365.530.7--0.62.70.5-----
TJL12-41.9656.422.6--0.63.87.30.7----
TJL12-54.7775.121.1--0.821-----
TJL12-64.5528.520.3-7.62.93.6352-8.7--
TJL12-73.6427.718.9-8.11.63.938.21.6----
TJL12-8p94.292.685.2---93.2-----
TJL12-915.825146.1----2.8-----
TJL12-109.2657.830.5---35.2---3.5-
TJL12-114.0849.436.5--2.463.1----2.7
TJL12-1212.826.141.4--0.65.226.6-----
TJL12-137.8227.39.8--0.9584.1-----
TJL12-1419.30.5----79.46.313.8----
TJL12-15f93.3324.643.424.6--3.31.4-2.6---
AVE-45.6228.38-7.851.2514.3510.224.53-8.703.502.70

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Yuan, Y.; Tang, S.; Zhang, S. Geochemical and Mineralogical Characteristics of the Middle Jurassic Coals from the Tongjialiang Mine in the Northern Datong Coalfield, Shanxi Province, China. Minerals 2019, 9, 184. https://doi.org/10.3390/min9030184

AMA Style

Yuan Y, Tang S, Zhang S. Geochemical and Mineralogical Characteristics of the Middle Jurassic Coals from the Tongjialiang Mine in the Northern Datong Coalfield, Shanxi Province, China. Minerals. 2019; 9(3):184. https://doi.org/10.3390/min9030184

Chicago/Turabian Style

Yuan, Yue, Shuheng Tang, and Songhang Zhang. 2019. "Geochemical and Mineralogical Characteristics of the Middle Jurassic Coals from the Tongjialiang Mine in the Northern Datong Coalfield, Shanxi Province, China" Minerals 9, no. 3: 184. https://doi.org/10.3390/min9030184

APA Style

Yuan, Y., Tang, S., & Zhang, S. (2019). Geochemical and Mineralogical Characteristics of the Middle Jurassic Coals from the Tongjialiang Mine in the Northern Datong Coalfield, Shanxi Province, China. Minerals, 9(3), 184. https://doi.org/10.3390/min9030184

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